Some New and Poorly Known Benthic Foraminifera from Late Maatrichtian Shallow-Water Carbonates of the Zagros Zone, Sw Iran

ACTA PALAEONTOLOGICA ROMANIAE (2016) V. 12 (1), P. 53-70

SOME NEW AND POORLY KNOWN BENTHIC FORAMINIFERA FROM LATE MAATRICHTIAN SHALLOW-WATER CARBONATES OF THE ZAGROS ZONE, SW IRAN

Felix Schlagintweit1* & Koorosh Rashidi2

Received: 8 August 2016 / Accepted: 20 August 2016 / Published online: 4 September 2016

Abstract Three new larger benthic foraminifera, Accordiella? tarburensis n. sp., Spirolina? farsiana n. sp., and Pseudonummoloculina kalatantarii n. sp. are described from the Late Maastrichtian of the Tarbur Formation, Zagros Zone, SW Iran. The rarely observed species Broeckinella arabica Henson, Broeckina cf. dufrenoyi (d´Archiac), Cu- villerinella? sp. and Fleuryana adriatica De Castro, Drobne & Gušić are also reported. All these forms occur in an internal carbonate platform facies (algal-foraminiferal wackestones-packstones) and are associated with numerous other larger benthic foraminifera (e.g., Loftusia, Neobalkhania, Gyroconulina, Omphalocyclus) and dasycladalean green algae.

Keywords: Late Cretaceous, larger benthic foraminifera, systematics, biostratigraphy

INTRODUCTION and Yaghmour, 2014) but several determinations however are incorrect and need revision. The Late Cretaceous Tarbur Formation, named after The first results and critical revisions on the micro- the village of Tarbur (Fars Province), and cropping out in palaeontology of the Tarbur Formation have been pub- the SW Zagros basin, represents a predominantly car- lished recently (Schlagintweit et al., 2016a in press, bonate lithostratigraphic unit that contains rich microfau- 2016b, 2017 in press). The present paper represents a na and microflora associated with rudists (James and further contribution to the study of the micropalaeonto- Wynd, 1965). It extends from the northwest to the south- logical inventory of the Tarbur Formation with the de- east of the Zagros basin along the western edge of the scription of the new larger and complex conical agglu- imbricated Zagros zone, between the main Zagros fault tinated foraminifera Accordiella? tarburensis n. sp., as and the Sabzposhan fault to the east (Alavi, 2004). The well as the porcelaneous taxa Spirolina? farsiana n. sp. Tarbur Formation overlies and interfingers (towards the and Pseudonummoloculina kalantarii n. sp. In addition, southwest) with the Gurpi Formation (Fig. 1). some other poorly known taxa are reported, some of them for the first time in Iran.

STUDIED SECTIONS

The foraminiferan-bearing samples studied are from two sections of the Tarbur Formation (Fig. 2): a) Mandegan section. The study area, located in the High Zagros Belt, is situat- ed north of Mount Dena, about 65 km south of the town Fig. 1 Lithostratigraphy of the Late Cretaceous of the Zagros Zone, Iran (excerpt and redrawn from the Stratigraphic Chart of of Semirom. The section of the Tarbur Formation is ex- Iran published by the Geological Society of Iran in 1995). posed about 10 km south of the village of Mandegan, and here named Mandegan section (Fig. 3). Here the Tarbur In the stratigraphic chart of Iran provided in 1995 by Formation shows a thickness of ~272 m and conformably the Geological Society of Iran, the Tarbur Formation is overlies the Gurpi Formation (Fig. 3c). The top of the assigned to the Campanian-Maastrichtian interval, fol- section is unconformably overlain by conglomerates of lowing the pioneer work of James and Wynd (1965). The the Pliocene Bakhtiari Formation (see Bahrami, 2009, for Maastrichtian rudist fauna of the Tarbur Formation has details). Based on the lithostratigraphy, the section has already been described by several authors (e.g., Douvillé, been divided into three units (from base to top): unit 1 is 1904; Kühn, 1932; Khazaei et al., 2010). In contrast, the dominated by thick-bedded limestones, unit 2 mostly micropalaeontological content of the Tarbur Formation is contains medium-bedded limestones with intercalated still poorly constrained. Some taxa of calcareous algae marly limestone layers, and unit 3 consists of marly lime- and benthic foraminifera have been mentioned and/or stones (see also Schlagintweit et al., 2016, and in press). illustrated in various recently published papers (Vaziri- The vertical distribution of the described taxa and some Moghadam et al., 2005; Afghah, 2009, 2010, 2016; Ma- index forms of larger benthic foraminifera in the Tarbur ghfouri-Moghaddam et al., 2009; Rajabi et al., 2011; Formation of the Mandegan section is shown in Figure 4. Abyat et al., 2012, 2015; Afghah and Farhoudi, 2012; The Greenwich coordinates of the section base are N 31º, Pirbaluti and Abyat, 2013; Pirbaluti et al., 2013; Afghah 25', 8.13'' and E 51º, 24', 34.58''.

______1Lerchenauerstr. 167, 80935 Munich, Germany, [email protected] 53 2Department of Geology, Payame Noor University, Po Box 19395-3697 Tehran, Iran, [email protected] Felix Schlagintweit & Koorosh Rashidi

positories. One part is deposited at the Bayerische Staats- sammlung für Paläontologie und historische Geology, Munich, under the official numbers SNSB-BSPG 2016 V 1 to V 20. All other thin-sections are deposited at the Ar- dakan Payame Noor University, Iran, collection Rashidi, under the original sample numbers with the prefixes Rt for the Mandegan section and Ng for the Naghan section.

SYSTEMATICS

The high-rank classification follows Pawlowski et al. (2013). For the low-rank classification see Kaminski (2014) for the agglutinating taxa, and Loeblich & Tappan (1987) for representatives of the Miliolida. For glossary, report to Hottinger (2006).

Phylum Foraminifera d’ Orbigny, 1826 Class Globothalamea Pawlowski et al., 2013 Order Textulariida Delage & Hérouard, 1896 Suborder Textulariina Delage & Hérouard, 1896 Superfamily Chrysalidinoidea Neagu, 1968 Family Chrysalidinidae Neagu, 1968 Remarks: Loeblich and Tappan (1987, p. 185) defined Fig. 2 Location map of the studied area. the Chrysalidinidae as possessing a wall “finely agglu-

tinated, canaliculate”. A different view was expressed by b) Naghan section. Banner et al. (1991) regarding the occurrence of proto- The studied area in the folded Zagros belt is located ap- canaliculate or canaliculated wall types as a facultative proximately 50 km south west of Naghan town near the species/genus criterion, of no suprageneric importance in Gandomkar village and is here named Naghan section. At the Chrysalidinidae. Canaliculi (or canaliculated) refer to this locality, the Tarbur Formation is underlain by the narrow, regular parallel arranged pores open to the exte- Gurpi Formation and overlying by the Paleocene Sachun rior (Banner et al., 1991, fig. 1b). Canaliculi were also Formation. Lithologically, the Gurpi Formation consists named parapores by Hottinger (2006) that per definition of dark, grey carbonatic shale with planktonic foraminif- “may be branching and anastomising”, ”may be laterally era. The Sachun Formation consists of gypsum, red interconnected” and end “blindly beneath an outer solid shales, anhydrite and some layers of carbonates. pavement”. In the chrysalidinid genera Praechrysalidina, The thickness of the Tarbur Formation at the Naghan Chrysalidina or Dukhania, canaliculi are sometimes re- section is about ~ 274 m. It is composed of medium to stricted to the last chambers only (see discussion in Ban- thick –bedded grey limestone, shales and marls and can ner et al., 1991). Banner et al. (1991) stressed that the be subdivided into 5 units development of canaliculi appeared in several line - unit 1 (99 m), red to yellow shales ages of benthic foraminifera and therefore concluded that - unit 2 (61 m), medium- to thick-bedded grey limestones the definition of suprageneric differences based on a spo- with Loftusia and rudist debris (calcarenites to calciru- radically appearing feature is useless. In the recent classi- dites) fication of agglutinated foraminifera of Kaminski (2014), - unit 3 (33 m), intercalation of grey shales and cream to the genus Accordiella with its non-canaliculate wall is grey, medium- to thick-bedded limestones (cacilutites and included in the Chrysalidinidae. calcarenite) Genus Accordiella Farinacci, 1962 - unit 4 (38 m), thick-bedded to massive, grey to cream- Type-species: Accordiella conica Farinacci, 1962 coloured limestones containing broken rudist shells and Accordiella? tarburensis n. sp. tests of Loftusia (calcarenite, calcilutite, calcirudite) Figs. 5a pars, 6–7, 8 pars. - unit 5 (~ 41.6 m), shales interbedded with medium- to 2016 agglutinated foraminifer chrysalinid – Afghah, fig. thick-bedded yellow limestones containing Loftusia 6d pars. fragments. Holotype: Axial section of the specimen illustrated in The vertical distribution of the described taxa and some Figure 6a, thin-section Rt 87. other index forms of larger benthic foraminifera in the Origin of the name: The species name refers to the vil- Tarbur Formation of the Naghan section is still under lage of Tarbur. investigation and therefore not presented here. The Type locality: Mandegan section (Fig. 2). Greenwich coordinates of the section base are N 31°47' Type level: Late Maastrichtian of the Tarbur Formation. 52" and E 50° 32' 53 ". Diagnosis: Medium conical possible representative of

Accordiella with distinct convex apertural face and wide- MATERIAL AND DEPOSITORY ly spaced, discrete pillars in the central part of the test.

Description: Test medium conical, low trochospiral, with The specimens illustrated in the present contribution 3 marginally overlapping chambers (per whorl) arranged are from various thin-sections stored at two different de- in up to 10 whorls and distinctly convex cone base. 54

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Fig. 3 a-b: Satellite (A, from google maps) and field views (b) of the Gurpi (GF) and Tarbur formations (TF) in the Mandegan area. The distance from left to right in A is ~4.7 km. Figure c: Conform boundary of Gurpi and Tarbur formations at the Mandegan section.

Details on the nepionic stage unknown. Spiral sutures structure (Farinacci, 1962, p. 7). Torre (1966, fig. 1) pre- clearly marked by test constrictions. Peripheral lumen of sented a schematic drawing of its central zone showing the chambers undivided (no exoskeletal elements). the presence of four horizontal plates per whorl. Stratig- Chamber height decreasing towards the centre of the test. raphy of A. conica is middle Coniacian to lowermost Adaxial area wide, distinctly convex, pierced by numer- middle Campanian (Frijia et al., 2015). For the occur- ous cribrate foramina and with numerous, discrete endo- rences of the species in the Mediterranean area see the skeletal pillars. Wall homogeneous very finely agglutinat- compilation in Radrizzani et al. (1987, tab.1). Compared ing, occasionally with thin dark outer layer (detectable in to A.? tarburensis, the central part of A. conica is densely the best preserved specimens). Dimorphism has not been occupied by narrowly spaced irregular endoskeletal ele- evidenced. ments (Fig. 8). According to Torre (1965), there are four Dimensions (mm): (Data for Accordiella conica in chambers per whorl in A. conica contrasting Farinacci brackets) (1962) describing the species as triserially coiled Test diameter (D): 0.8-1.4 mm (0.6-1.0 mm) throughout. In fact, four chambers are discernible in some Test height (H): 0.7-1.4 mm (0.8-1.2 mm) specimens illustrated by Farinacci (1962, pl. 2, fig. 6, and Ratio D/H: 0.8-1.2 (mostly ~1.1) ?some specimens in pls. 4-5). So the more complicated Apical angle: 60-90 degrees; mostly ~80 degrees (about central part of A. conica compared to A.? tarburensis 80 degrees) might by an effect of more chambers per whorl in the Number of whorls: 5-10 (8-12) former. Generally, the shape of the pillars of both taxa is Number of whorls per last 0.5 mm (measured along the different. In A. conica these are irregularly thickening, cone mantel line = cml, see Hottinger & Drobne, 1980, undulating, and merging whereas in A.? tarburensis they fig. 3): 2 to 4 are straight, cylindrical, with a slight widening at the base Thickness of pillars (central part): 0.025-0.04 mm. and top. With thickness of ~0.017 mm to ~0.035 mm Comparisons: The type-species Accordiella conica Fari- (own observations), the pillars of A. conica are more nacci, 1962 (upper Cretaceous of Italy) differs from A.? slender compared to A.? tarburensis. Due to the lack of tarburensis by its broad axial region with an endoskele- horizontal plates in the central zone the generic position ton consisting of numerous, fine horizontal plates that are of the species A.? tarburensis is uncertain. An Accordiel- interconnected by vertical pillars or buttresses (Farinacci, la-type larger benthic foraminifer has been recently de- 1962; Torre, 1966; Loeblich and Tappan, 1987, p. 151) scribed as Pseudoaccordiella ayaki Gallardo-Garcia & (see Fig. 8). In the original description, the central part of Serra-Kiel (in Serra-Kiel et al., 2016) from the Late Eo- Accordiella was described as possessing a labyrinthic cene (Priabonian) of Oman and Yemen (see Fig. 8). 55

Felix Schlagintweit & Koorosh Rashidi

Fig. 4 Vertical distribution of the described taxa and some index forms of larger benthic foraminifera in the Tarbur Formation of the Mandegan section.

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Pseudoaccordiella is characterized by a pseudokerio- Suborder Biokovinina Kaminski, 2004 thekal wall texture, a triserial nepionic, and a biserial Superfamily Biokovinoidea Gušić, 1977 neanic stage. The structure of the central part of Pseudo- Family Charentiidae Loeblich & Tappan, 1985 accordiella and Accordiella is directly comparable. The Genus Fleuryana De Castro, Drobne & Gušić, 1994 tests of Pseudoaccordiella are larger than A. conica and Fleuryana adriatica De Castro, Drobne & Gušić, 1994 A.? tarburensis (height up to 2.7 mm, measured from Fig. 10 Serra-Kiel et al., 2016, fig. 30.4). *1994 Fleuryana adriatica n. gen., n. sp. – De Castro et al., p. 133, pls. 1–4, figs. 3-5, 7–8. Order Loftusiida Kaminski & Mikhalevich, 2004 1998 Fleuryana adriatica De Castro, Drobne & Gušić – Suborder Loftusiina Kaminski & Mikhalevich, 2004 Caffau et al., fig. 5.2–3. Superfamily Loftusioidea Brady, 1884 Remarks: In the original description, information on the ? Family Cyclamminidae Marie, 1941 suprageneric taxonomy of Fleuryana was not provided. Subfamily Pseudochoffatellinae Loeblich & Tappan, In the two classifications of agglutinated taxa provided by 1985 Kaminski (2004, 2014), the genus Fleuryana is not in- Genus Broeckinella Henson, 1948 cluded. Because of its morphology as well as the finely Remarks: It should be mentioned here that in the defini- perforate wall structure, De Castro et al. (1994) discuss in tion of the families Cyclamminidae and Spirocyclinidae, detail similarities and differences to Montcharmontia De Albrich et al. (2015, p. 255) where not following the clas- Castro, a genus included in the family Charentiidae sification of Kaminski (2014). According to these authors (Loeblich and Tappan, 1987; Kaminski, 2014). We pro- “the genera with polygonal subepidermal patterns should pose to assign Fleuryana to this family. be ascribed to the Family Spirocyclinidae instead of the In the Mandegan section, Fleuryana adriatica occurs in Cyclamminidae”. In this definition, the genus Broeckinel- the upper part of unit 1 persisting into the upper part of la possessing a polygonal subepidermal pattern (e.g., Fig. unit 2. Originally described from the uppermost Maas- 9d, left side) should be included in the Spirocyclinidae. trichtian, its first appearance is somewhere in the middle Broeckinella arabica Henson, 1948 part of the Campanian (Fleury, 2014, fig. 3). This en- Fig. 9a–e larged stratigraphic range should be taken into considera- *1948 Broeckinella arabica n. gen., n. sp. – Henson, p. tion as in some papers F. adriatica is erroneously consid- 93, pl. 7, fig. 6, text-fig. 13a-c. ered as a late Maastrichtian marker taxon (e.g., Mikuž et 1978 Broeckinella arabica Henson – Cherchi and al., 2012). The occurrence of F. adriatica in the Tarbur Schroeder, p. 514, fig. 1 A-C. Formation is the first record of this taxon in Iran. Accord- 2004 Dicyclina schlumbergeri – Khosrow Tehrani and ing to our knowledge it is the easternmost record so far. Afghah, pl. 2, fig. 4. 2008 Dicyclina schlumbergeri – Khosrow Tehrani et al., Class Tubothalamea Pawlowski et al., 2013 pl. 1, fig. 6. Order Miliolida Delage & Hérouard, 1896 Description: Test compressed, with numerous chambers Superfamily Soritoidea Ehrenberg, 1839 rapidly increasing in width so that the test becomes Family uncertain slightly flabelliform (Fig. 9a–b). Information on the ini- Genus Broeckina Munier-Chalmas, 1882 tial part is not available in our sections (for details see Remarks: Loeblich & Tappan (1987) included Broecki- Cherchi and Schroeder, 1978). The wall is very finely na in the Meandropsinidae Henson. Following the emen- agglutinating and the chamber margins are subdivided by dation of this family by Hottinger & Caus (2009), exoskeletal elements, both vertical and horizontal result- Broeckina lacking a diaphanous umbo, should be re- ing in a polygonal meshwork (or pattern) (Fig. 9a, d). moved from the Meandropsinidae as remarked by Con- Remarks: Broeckinella arabica is the type-species of the sorti et al. (2016) instead remaining in the superfamily genus Broeckina described by Henson (1948) from the Soritoidea. The family status however is still uncertain. Maastrichtian? of Qatar. According to the critical litera- Broeckina cf. dufrenoyi (d’Archiac, 1854) ture review of Cherchi and Schroeder (1978) there is ob- Fig. 11 viously no verified other record of this taxon besides its *1854 Cyclolina dufrenoyi n. sp. – d’ Archiac, p. 205, pl. type-locality. In the Tarbur Formation of the Mandegan 2, figs. 1a–d. section, it was rarely observed in samples Rt 64, 68, 78, 1882 Broeckina dufrenoyi (d’ Archiac) – Munier- 85, and 104, referring to the upper most part of unit 1, Chalmas, p. 471. and persisting into unit 3 (Fig. 4). The material of 1975 Broeckina dufrenoyi (d’ Archiac) – Cherchi and Broeckinella arabica from the Tarbur Formation does not Schroeder, p. 5, pl. 1, figs. 1–6, pl. 2, figs. 1–3, pl. 4, figs. include centered sections. Data on the test dimensions 2, 4–6. only comprise incomplete sections attaining a maximum Description: Test flat discoidal, with annular chambers size of 2.4 mm. B. arabica was figured as Dicyclina displaying an exoskeleton of radial partitions. Test wall is schlumbergeri from the Maastrichtian of the Tarbur For- porcelaneous. Due to the lack of adequate sections, in- mation by Khosrow Tehrani and Afghah (2004) and the formation on the initial part is not available (for details Maastrichtian of the Amiran Formation (SW Iran, Zagros see Cherchi and Schroeder, 1975). The specimens attain Zone) where the authors distinguished a Loftusia- diameter of up to 2.6 mm, and a thickness of up to 0.15 Dicyclina assemblage zone. On the other side, Dicyclina mm. cf. schlumbergeri is common in the upper part of the Tar- Remarks: Broeckina gassoensis from the middle Coni- bur Formation (Fig. 4). acian of Spain differs from Broeckina dufrenoyi by its

Felix Schlagintweit & Koorosh Rashidi

Fig. 5 Microfacies of some charactersistic samples. a Packstone with benthic foraminifera Gyroconulina columellifera Schroeder & Darmoian (G), Omphalocyclus macroporus (Lamarck) (O), Laffiteina sp. (L), Minouxia/Tetraminouxia (M), Accordiella? tarburensis n. sp. (Z), Sirtina (S). Thin-section Rt 105. b Wack- estone with Loftusia sp. (L), and Broeckina cf. dufrenoyi (d’Archiac) (B), thin-section Rt 113.

smaller size and different evolution of the septula (for Remarks: A modern generic diagnosis was provided by further details see Caus et al., 2013). According to Caus Vicedo et al. (2011). et al. (2013), the type-species B. dufrenoyi should be re- Cuvillierinella? sp. stricted to the late Santonian–early Campanian. The oc- Fig. 12 currence of Broeckina cf. dufrenoyi (d’Archiac, 1854) in Remarks: Rare and very poorly preserved specimens the late Masstrichtian of the Tarbur Formation is there- were observed in a comparatively narrow interval of unit fore of special interest. It is recorded from both 3 of the Mandegan section. The oblique to subaxial sec- Mandegan and Naghan sections where it appears in the tion show general similarities to Cuvillierinella salentina uppermost part of the sections. described by Papetti & Tedeschi (1965) from the Campa- Genus Cuvilierinella Papetti & Tedeschi, 1965 nian of southern Italy (see also Vicedo, 2011). Cuvillier- 58

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Fig. 6 Accordiella? tarburensis n. sp., Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a–d, f, h–m Axial and subaxial sections. e, g Oblique sections. Thin-sections: Rt 87 (a, g), Rt 67-3 (b), Rt 61-1 (c), SNSB-BSPG 2016 III-4 (d), Rt 89-3 (e), Rt 113-2 (f), Rt 67 (h), Rt 70 (i), Rt 105 (j), Ng 189 (k), Rt 82 (l), Rt 73 (m). inella is known from the middle Campanian to early to three planispirally coiled whorls that may also slightly Maastrichtian (e.g., Fleury, 2014, fig. 3; Vicedo et.al., oscillate. Chamber lumen semi-lunate in equatorial and 2011), and its occurrence in the late Maastrichtian is de- rounded-arched in axial sections. Rectilinear adult part batable. with few chambers. Foramina simple in the planispiral Genus Spirolina Lamarck, 1804 part, becoming most likely cribrate with small projections Spirolina? farsiana n. sp. (teeth?) in the uncoiled part. Figs. 13–14 Description: Test planispirally coiled in two to three Holotype: Fig. 13b, Thin-section Rt 67-2. whorls, each with an increasing number of chambers. Origin of the name: The species name refers to the Fars Early stage most likely involute then biumbonate and province of Iran. semi-involute. Test periphery is rounded. Planes of coil- Type locality: Mandegan section (Fig. 2). ing may slightly oscillate. As discernible in equatorial Type level: Late Maastrichtian of the Tarbur Formation. sections, the sutures are barely if ever discernible at the Diagnosis: Possible representative of Spirolina with two test surface. There are 8 to 10 chambers in the last en-

Felix Schlagintweit & Koorosh Rashidi

Fig. 7 Accordiella? tarburensis n. sp., Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a–f Oblique transverse sections. g–i, k–l Oblique sections. j Broken axial section. Thin-sections: SNSB-BSPG 2016 III-8 (a–c), Rt 68 (d–e), Rt 82 (f), Rt 87 (g), Rt 71 (h), Rt 64 (i), Rt 61-1 (j), Rt 70 (k), Rt 73 (l). Abbreviations: f = foramen, pi = pillar. rolled whorl and then the test becomes uncoiled, rectilin- earance (structural differences enhanced by diagenetic ear, more or less cylindrical in the adult part (with up to 7 alteration? agglutinated particles?). chambers). In equatorial sections, the outline of the Remarks and comparisons: The genus Spirolina has chamber lumen is mostly semi-lunate, and rounded- been critically reviewed by Tronchetti and Grosheny arched in axial sections. The septa are inclined. The fo- (1992) concluding that all Mesozoic representatives are ramina in the planispiral stage are simple, areal, with sev- highly doubtful, and that S. cretacea Tronchetti & Gro- eral tiny protrusions (teeth?) in the uncoiled stage (Fig. sheny from the Santonian of France would be the only 13d, g). The wall is porcelaneous, imperforate. The inner Mesozoic Spirolina and therefore its oldest record. Note part of the wall always is dark homogeneous, whereas the that Loeblich and Tappan (1987) regarded the genus as outer part often displays a light-grey finely grumbly app- Eocene to Holocene. Spirolina cretacea Tronchetti &

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Fig. 8 Stratigraphic distribution and general comparison of Accordiella conica Farinacci, Accordiella? tarburensis n. sp., and Pseudoaccordiella ayaki Gallardo-Garcia & Serra-Kiel, (from Serra-Kiel et al., 2016, fig. 30.3 and 30.7).

Grosheny, is different from Spirolina? farsiana above all Subfamily Hauerininae Schwager, 1876 due to its chamber shape (more or less pyriform), the well Genus Pseudonummoloculina Calvez, 1988 expressed sutures, reduced number of chambers, and the Remarks: Calvez (1988) established the genus Pseu- costate surface ornamentation (Tronchetti and Grosheny, donummoloculina (type-species Pseudonummoloculina 1992, for details). The taxonomic uncertainty of the aurigerica, Albian of the Pyrenees) for “nummoloculi- Maastrichtian taxon from Iran is due to the lack of test nas” with a notched aperture (= an aperture bordered by a ornamentation and especially details on the aperture that series of notches protruding from the floor and roof of the is controversely discussed in the literature. According to chambers). The widespread Cenomanian “nummoloculi- Loeblich and Tappan (1987), Spirolina displays a termi- nas” were thereafter regarded as Pseudonummoloculina nal, rounded aperture, whereas the allied genus Dendriti- sp. by De Castro (1987) since they show a “wavy mar- na d’ Orbigny (both Eocene to Holocene) has a dendritic gin” simulating a cribrate aperture. Likewise, the restudy (or stellate) aperture. A single opening as apertural type of the Mexican material of Nummoloculina heimi Bonet for Spirolina was recently also remarked by Sirel et al., by Hottinger et al. (1989) did not substantiate the exist- (2013). Tronchetti and Grosheny (1992, p. 397) on the ence of an aperture with a tooth, in contrast to the emen- other hand united forms with either a rounded terminal dation provided by Conkin & Conkin (1958), but accord- aperture with numerous small teeth-like projections or ing to the former, the aperture “clearly show rows of forms with ramified, simple or multiple aperture. It is notches in the distal margin”. Owing to these structural worth mentioning that S. cretacea possesses a multiple differences, Hottinger et al. (1989: p. 104) introduced the aperture with small teeth. An equivalent aperture seems new combination Pseudonummoloculina heimi (Bonet) to be present also in S.? farsiana. The presence of a den- concluding that “pseudonummoloculinid species exist tritic aperture in S.? farsiana however cannot be excluded from Albian to Senonian in at least three neighboring due to the lack of transverse section cutting the foramina bioprovinces (Caribbean, Pyrenean and western Te- in the uncoiled part. The dendritic foramina/aperture in thys)”. In a contribution on Lower-Middle Cretaceous the Paleogene taxon Paraspirolina gigantea for example foraminifers from deep-sea drilling legs, Arnaud- shows very similar projections above the septa in longi- Vanneau & Sliter (1995) state, “the genus Pseudonummo- tudinal section through the uncoiled part (Fleury, 1997, loculina is represented by three species: the type-species e.g., pl. 1, fig. 23, penultimate chamber!) as observed in P. aurigerica Calvez (Albian of Spain), P. heimi (Bonet) S.? farsiana (Fig. 13d, g). (Cenomanian of Mexico) and P. robusta (Torre) (Coni- We note some morphological similarities of Spirolina? acian or Santonian of Italy)”. Excluded are Nummo- farsiana to the early Paleogene Kayseriella decastroi loculina regularis Philippson (late Cretaceous of Austria, Sirel. This species differs from the former by its thick see discussion in Schlagintweit, 2008, for details) and apertural tooth and peristomal rims (Sirel, 1999). Last but Nummoloculina irregularis Decrouez & Radoičić, 1977. not least, S.? farsiana displays also affinities to represent- The latter possessing an ophthalmidid type of coiling atives of Pseudorhapydionina De Castro (e.g., De Castro, different from Pseudonummoloculina. 1985; Consorti et al., 2016), but lacking septula. Superfamily Miliolacea Ehrenberg, 1839 Pseudonumoloculina kalantarii n. sp. Family Hauerinidae Schwager, 1876 Fig. 15 61

Felix Schlagintweit & Koorosh Rashidi

Fig. 9 Broeckinella arabica Henson (a–e) and Dicyclina cf. schlumbergeri Munier-Chalmas (f), Late Maastrichtian Tar- bur Formation of Mandegan section, Zagros Zone, SW Iran. a–d Oblique equatorial sections, partly fragmentary, in some parts crossing the subepidermal network of beams and rafters (e.g., left side of d). e Oblique section of Broeckinella arabica, comparable to the section erroneously illustrated as “Dicyclina schlumbergeri” by Khosrow Tehrani et al., 2008 in pl. 1, fig. 6. f Dicyclina cf. schlumbergeri Munier-Chalmas, subaxial section. Thin-sections: Rt 104 (a), Rt 64 (b), Rt 78 (c), Rt 85 (d), Rt 68 (e), SNSB-BSPG 2016 III-4 (f). Scale bars 0.5 mm.

Holotype: Slightly oblique axial section of a juvenile egg-shaped, slightly biumbilicate test, and rounded mar- specimen (showing notched aperture) illustrated in Figure gin. The test is streptospirally coiled initially (3 to 4 15k (and detail in Fig. 15n). Thin-section NG 85. whorls) then oscillating to almost planispiral (up to 5 Origin of the name: The species name is dedicated to whorls). Chambers elongated along the coiling, low and Amir Kalantari, micropalaeontologist of the National only gradually increasing in height. Iranian Oil Company for his contributions to the micro- Description: Test ovate, with slight biumbilical depres- palaeontology of Iran. sion and broadly rounded periphery. First whorls strep- Type locality: Naghan section (see Fig. 2) tospirally coiled, later planes of coiling become more and Type level: Late Maastrichtian of the Tarbur Formation. more regular to almost planispiral, resulting in an overall Diagnosis: Representative of Pseudonummoloculina with sigmoid arrangement when observed in axial sections 62

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Fig. 10 Fleuryana adriatica De Castro, Drobne & Gušić, Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a, f Equatorial sections. b–c Oblique sections. d Broken oblique section. e Axial section. Thin-sections: Rt 87 (a), SNSB-BSPG 2016 III-7 (b–c), Rt 82 (d), Rt 68 (e), Rt 70 (f).

Fig. 11 Broeckina cf. dufrenoyi (d’Archiac), Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a Fragmentary equatorial section showing septules. b–c Oblique sections showing septula. d Subaxial section. Thin-sections: SNSB-BSPG 2016 III-16 (a–b), SNSB-BSPG 2016 III-17 (c), Rt 113-2 (d).

Fig. 12 Cuvillierinella? sp., Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a Oblique section close to axial plane. b–c Subaxial sections. sl = septulum. Thin-sections: Rt 100 (a), SNSB-BSPG 2016 III-10 (b), SNSB-BSPG 2016 III-18 (c).

Felix Schlagintweit & Koorosh Rashidi

Fig. 13 Spirolina? farsiana n. sp., Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a Oblique equatorial section of specimen with uncoiled adult part. b Slightly oblique equatorial section with few uncoiling chambers; holotype specimen. c Subaxial section: Note changing growth direction of enrolled part. d Detail of e showing foramina with lip-like projections. e, f “Axial” section of the uncoiled part. g–h Subaxial sections. Note teeth-like projections in g (arrow). i, fragmentary oblique section. Thin-sections: Rt 67-3 (a, e–d), Rt 67-2 (b, h), SNSB-BSPG 2016 III-1 (c, g, i), SNSB-BSPG 2016 III-8 (f).

(Fig. 15h). Septa inclined and rather short delimiting Equatorial diameter (ed): up to 2 mm chambers that are greatly elongated along the coiling di- Axial diameter (ad): up to 0.9 mm rection and that only gradually increase in height. Num- Ratio ad/ed: 0.6 to 0.7 ber of chambers per whorl unclear. Wall calcareous im- Comparisons: The differences to the other species of perforate, porcelaneous, possibly with some incorporated Pseudonummoloculina can be summarized as follows. (agglutinated) grains (e.g., Fig. 15j, g). Foramina and Pseudonummoloculina aurigerica Calvez, 1988 (Albian aperture with numerous short notches, irregular in shape, of Spain): The planispiral stage of the type-species is protruding from the chamber roof and floor (Fig. 15l–n) reduced with only 1 ½ to 2 ½ whorls compared to up to 5 Dimensions (in mm):

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran

Fig. 14 Spirolina? farsiana n. sp., Late Maastrichtian Tarbur Formation of Mandegan section, Zagros Zone, SW Iran. a Subaxial section. b–c, f Equatorial section, partly oblique. d–e, g Subaxial, slightly oblique sections. Thin- sections: Rt 67-3 (a, e), Rt 70 (b, f), Rt 86 (c), SNSB-BSPG 2016 III-3 (d), Rt 84 (g). in P. kalantarii. Also the size is reduced (ed up to 1.3 tively SBZ 2 to 3 of Serra-Kiel et al. (1998), noting a mm, ad up to 0.73 mm). forthcoming description. In this connection reference was Pseudonumoloculina heimi (Bonet, 1956) (Cenomanian made to Dieni et al. (1985, pl. 17, fig. 7). One illustration of Mexico): With its numerous whorls (up to 5), and size of this taxon can be found in Drobne and Cosovic (2009, (ed up to 2.16 mm), P. heimi is close to P. kalantarii. P. fig. 4, Pseudonummoloculina n. sp.). A difference of P. heimi is different from the former in its compressed dis- sopadensis to P. kalantarii might be the reduced size, and coidal test (ratio ad/ed 2.45 to 3.6, as measured from test morphology indicated as spherical to slightly nauti- Conkin and Conkin (1958, fig. 1-25). loid in Drobne et al. (2005). Pseudonummoloculina robusta (Torre, 1966) (Coniacian or Santonian of Italy): In P. robusta, wall thickness near- MICROFACIES AND FAUNAL ASSOCATIONS OF ly equals the width of the chamber lumen, given rise to THE DESCRIBED TAXA the species name. With maximum size of 1.025 mm, P. robusta is much smaller than P. kalantarii. A further dif- The taxa described and reported in the present paper were ference is the inclination of the axes of successive cham- observed in foraminiferan-dasycladalean wackestones to ber within a whorl as discernible in equatorial sections packstones, referring to a soft substrate and very low wa- (Torre, 1966, pl. 3, fig. 3) whereas in P. kalantarii they ter energy in a shallow protected lagoon. In the Tarbur are more or less in line. Formation this facies is characterized by the association Pseudonummoloculina sopadensis Drobne, Premru & of agglutinated conical foraminifera (Orbitolinidae indet., Ogorelec, 2005, nom. nud. (Thanetian of Slovenia): In a Gyroconulina, Dictyoconella), miliolids [among complex congress abstract, Drobne et al. (2005) introduced the taxa such as Broeckina cf. dufrenoyi (d’ Archiac), and new species Pseudonummoloculina sopadensis (with test Tarburina zagrosiana Schlagintweit, Rashidi & Barani], sizes of up to 1.5 mm) from the Thanetian of Slovenia. and dasycladalean algae. Except for the lack of alveo- So far no valid description and typification were provided linids, and the presence of rudists, this association can and therefore currently the taxon fails to confirm to arti- palaeoecologically be compared to similar associations of cle 13 of the International Code of Zoological Nomencla- the Paleogene (e.g., Vecchio and Hottinger, 2007, fig. 5), ture (= nomen nudem). Nonetheless, P. sopadensis was e.g., the so-called “Spirolina facies” of the Mediterranean included in the list of the shallow benthic zones, respect- area (e.g., Sartoni and Crescenti, 1962; Radoičić, 1995;

Felix Schlagintweit & Koorosh Rashidi

Fig. 15 Pseudonummoloculina kalantarii n. sp., Late Maastrichtian Tarbur Formation of Naghan section, Zagros Zone, SW Iran. a–b Equatorial sections. c–d, f–g, j Oblique sections. e, h–i, k Oblique axial to subaxial sections. l–n Details from i–k showing notched aperture in the last whorls. Holotype specimen in k (detail in n). Notched apertures are also discernible in d and f (arrows), and a?. Thin-sections: TB 82 (a), NG 81 (b), NG 83 (c, h–i, l), NG 86 (d), NG 83-2 (e–f, j, m), NG 85 (g, k, n).

Fleury, 1997; Barattolo et al., 2000). As a depth trend, the highly diverse and includes (in alphabetical order) be- Mandegan section displays a shallowing upwards sedi- sides the taxa illustrated in the present paper: Antalyna mentary succession with the remarked association occur- korayi Farinacci & Köylüoglu, Cuneolina sp., Dicyclina ring in the upper part. Amongst the Dasycladales we note cf. schlumbergeri Munier-Chalmas, Dictyoconella mini- the occurrence of Pseudocymopolia anadyomenea (El- ma Henson, Elazigella? sp., Fallotia aff. jacquoti Dou- liott), Pseudocymopolia? sp., Salpingoporella pasmanica villé, Gyroconulina columellifera Schroeder & Darmoian, Radoičić (see Schlagintweit et al., 2016b) and other taxa Laffiteina monodi Marie, Loftusia harrisoni Cox, currently under study. The foraminiferan association is Loftusia coxi Henson, Loftusia morgani Douvillé, Missis- 66

Some new and poorly known benthic foraminifera from Late Maastrichtian shallow-water carbonates of the Zagros zone, SW Iran sippina? binkhorsti (Reuss), Nezzazatinella? cf. picardi ers Sylvain Rigaud (Singapore) and Lorenzo Consorti (Henson), Neobalkhania bignoti Cherchi, Radoičić & (Barcelona). Schroeder, Elphidiella? cretacea (Pérébaskine), Om- phalocyclus macroporus (Lamarck), Orbitolinidae indet., REFERENCES Tarburina zagrosiana Schlagintweit, Rashidi & Barani, Valvulina? sp. 1 Sirel. It must be stressed, that not all the Abyat, A., Afghah, M., Feghhi, A., 2012. Stratigraphy above listed taxa are co-occurring in the same sample. and foraminiferal biozonation of Upper Cretaceous sediments in southwest Sepid Dasht, Lurestan, Iran. STRATIGRAPHY Australian Journal of Basic and Applied Sciences, 6 (13): 18-26. Based on larger benthic foraminifera [e.g., Loftusia Abyat, A., Afghah, M., Feghhi, A., 2015. Biostratigraphy ssp., Siderolites calcitrapoides Lamarck, Gyroconulina and lithostratigraphy of Tarbur Formation (Upper columellifera Schroeder & Darmoian, Omphalocyclus Cretaceous) in southwest of Khorram Abad (south- macroporus (Lamarck)], the studied sections are Maas- west Iran). Carbonates and Evaporites, 30 (1): 109- trichtian in age (Schlagintweit et al., 2016b, and in press, 118. with references therein). We also want to stress the occur- Afghah, M., 2009. New investigations of the Tarbur rence of the lamellar perforate Maastrichtian taxon Formation lithostratigraphy in the review of type sec- Laffiteina monodi Marie (e.g., Hottinger, 2014) in the tion and its correlation with Kuh-e Tir section. Journal uppermost part of the Mandegan section (samples Rt 90 of Sciences Islamic Azad University, 19 (73): 183- to Rt 111) (Fig. 16). Neobalkhania bignoti was originally 196. described by Cherchi et al. (1991) from the Late Maas- Afghah, M., 2010. Biozonation and biostratigraphic lim- trichtian of Croatia. its of the Tarbur Formation around Shiraz (SW of Iran). PhD Thesis University of Münster, 171 p. Online:http://repositorium.uni-muenster.de/document/ miami/e11da774-0bf2-45f5-a790- 2a2dc0caad2a/diss_afghah.pdf Afghah, M., 2016. Biostratigraphy, facies analysis of Upper Cretaceous – Lower Paleocene strata in South Zagros Basin (southwestern Iran). Journal of African Earth Sciences, 119: 171-184. Afghah, M., Farhoudi, G., 2012. Boundary between Up- per Cretaceous and Lower Paleocene in the Zagros

Mountain Ranges of southwestern Iran. Acta Geolog- Fig. 16 Lamellar perforate foraminifera Laffiteina monodi ica Sinica, 86 (2): 325-338. Marie. a Oblique section, thin-section Rt 100-2. b Afghah, M., Yaghmour, S., 2014. Biostratigraphy study Subaxial section, thin-section Rt 90. of Tarbur Formation (Upper Cretaceous) in Tang-E Kushk and east of Sarvestan (SW of Iran). Journal of Cherchi et al. (1991, p. 288) also noted its occurrence in Earth Science, 25 (2): 263-274. time-equivalent strata from Greece, concluding that N. Alavi, M., 2004. Regional stratigraphy of the Zagros bignoti represents “an excellent marker of this time inter- foldthrust belt of Iran and its proforeland evolution. val” (see also Fleury, 2014, Fig. 3). A Late Maastrichtian American Journal of Science, 304: 1-20. age for the upper part of the Tarbur Formation, which Albrich, S., Boix, C., Caus, E., 2015. Selected agglutinat- contains the new taxa Accordiella? tarburensis, Spiroli- ed larger foraminifera from the Font de les Bagasses na? farsiana, Pseudonummoloculina kalantarii and other unit (Lower Campanian, southern Pyrenees). Carnets foraminifers reported in this paper, can be concluded. de Géologie, 15 (18): 245-267. This conclusion is also in line with the occurrence of Si- Archiac, A., d’, 1854. Coupe géologique des environs des derolites calcitrapoides Lamarck in the lower samples of Bains-de-Rennes (Aude), suivi de la description de the Mandegan section (some meters above the boundary quelques fossiles de cette localité. Bulletin de la to the underlying Gurpi Formation, see Fig. 4), since the Société géologique de France, sér. 2, 2: 185-230. first occurrence of this taxon is latest early Maastrichtian Arnaud-Vanneau, A., Sliter, W.V., 1995. Early (according to Robles Salcedo, 2014). This implies that Cretaceous shallow-water benthic foraminifers and the Gurpi Formation ranges into the Maastrichtian at the fecal pellets from leg 143 compared with coeval fau- Mandegan section. nas from the Pacific Basin, Central America, and the Tethys. In: Winterer, E.L., Sager, WW., Firth, J.V., ACKNOWLEDGEMENTS Sinton, J.M. (Eds.); Proc. Ocean Drilling Program, Scientific results, 143: 537-564. Katica Drobne (Ljubljana) is thanked for providing litera- Bahrami, M., 2009. Sedimentology and paleogeography ture, Mariano Parente (Naples) for images of Accordiella of the Bakhtyari conglomeratic formation at Ghalat conica from the upper Cretaceous of Italy for compari- and Garu-Charmakan Mountains, NW of Shiraz, Iran. son, and Josep Serra-Kiel (Barcelona) for further infor- Journal of Geology, Geophysics and Geosystems, 3 mation on Pseudoaccordiella. The manuscript benefitted (1): 1-10. from the constructive and helpful remarks of the review- Banner, F.T., Simmons, M.D., Whittaker, J.E., 1991. The Mesozoic Chrysalidinidae (Foraminifera, Textularia- 67

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